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ta, warmer lower strata), a positive temperature gradient is developed (effect of friction), when the water tends to infiltrate the ground gradually, loosening and carrying away boulders and pebbles. A thermal surface-gra- dient is now added to the physical riverbed-gradient. A further increase in run-off velocity and the power to shift pebbles, gravel and sediment ensues. Once the present positive temperature gradient again becomes negative, bends in the river are formed in the lower reaches through turbulence, and thus a mechanical deceleration in the rate of flow occurs. Suspended sedi- ment is deposited and the oncoming water-masses become backed up. The result: flooding. In Case 2, if saturation of the groundwater basin occurs as a result of a stable positive temperature gradient, then groundwater (springwater) that now surfaces is colder than the ground strata lying directly beneath it. The temperature gradient has been reversed and has become negative again. Rapid drainage of the heavy water-masses follows. As a result of relatively low temperatures in the ground, cold, heavy, excess water from the Earth's interior now drains off, achieving a positive condition only gradually, because the specifically-heavier water warms up very slowly. Since in the upper third of the catchment area the slope of the riverbed is usually extremely steep, turbulence is created, and hence bends in the more hori- zontal parts of the river are formed. The further transition from a negative to a positive temperature gradient therefore takes place very slowly, and the incidence of strong turbulence again leads to excessively sharp horizontal bends and to the deposition of boulders, pebbles and sediment, the gouging of pot-holes and the disloca- tion of the channel bed through mechanical action. The immediate result of this type of discharge is a widening of the channel, a heaping up of broad banks of boulder-gravel, and evaporation or subsidence of water in the churned-up riverbed. In this process the riverbed has again been exposed to the influence of external temperature (already typical of alpine flow- regimes, and always associated with an asymmetrical profile - a deepened Loew describes the following case: 'It was in July 1902 or 1903, the exact date and hour escapes the following example available: 'My house lies high up on a mountain, and naturally water is of major importance. As happens every year the so- called 'May-water' appeared in 1911 just next to my house. 1911 was a conspicuously dry year. With much anxiety I kept a constant watch on the little streamlet. With increasing dryness, the spring sud- denly began to discharge about 20 paces higher up the mountain. The drier the season, the more abun- pen on that day, however, but only after the rain had dant the water from this new, higher-lying spring, and the warmer the temperature and the hotter the summer, the colder the water was." From a letter by Viktor Schauberger to the editor of Die Wasserwirtschaft, Vol 7,1931, p.106. - Ed. me. The place: Bukowina, the catchment area of the Moldawitza, a large enclosed area of primeval forest with typical primeval forest cover. After a prolonged period of dry weather a general and persistent rain- fall of varying intensity occurred, lasting about six days. I remember very distinctly that on the last day of rain general flooding was expected. It did not hap- stopped - and when it actually did flood, it did so with unparalleled force, as though the forest had suddenly lost its ability to retain water.'Mr Thaler, the Minister of Agriculture, also kindly madePDF Image | The Water Wizard
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